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The Response of the Antarctic Oscillation to Increasing and Stabilized 15 MAY 2003 CAI ET AL. 1525 The Response of the Antarctic Oscillation to Increasing and Stabilized Atmospheric CO2 WENJU CAI AND PETER.H.WHETTON CSIRO Atmospheric Research, Aspendale, Victoria, Australia DAVID J. KAROLY School of Mathematical Sciences, Monash University, Victoria, Australia (Manuscript received 6 June 2002, in ®nal form 14 October 2002) ABSTRACT Recent results from greenhouse warming experiments, most of which follow the Intergovernmental Panel on Climate Change (IPCC) IS92a scenario, have shown that under increasing atmospheric CO 2 concentration, the Antarctic Oscillation (AAO) exhibits a positive trend. However, its response during the subsequent CO 2 stabi- lization period has not been explored. In this study, it is shown that the upward trend of the AAO reverses during such a stabilization period. This evolution of an upward trend and a subsequent reversal is present in each ensemble of three greenhouse simulations using three versions of the CSIRO Mark 2 coupled climate model. The evolution is shown to be linked with that of surface temperature, which also displays a corresponding trend and reversal, incorporating the well-known feature of interhemispheric warming asymmetry with smaller warming in the Southern Hemisphere (smaller as latitude increases) than that in the Northern Hemisphere during the transient period, and vice versa during the stabilization period. These results indicate that once CO 2 con- centration stabilizes, reversal of the AAO trend established during the transient period is likely to be a robust feature, as it is underpinned by the likelihood that latitudinal warming differences will reduce or disappear. The implication is that climatic impacts associated with the AAO trend during the transient period may be reversible if CO2 stabilization is achieved. 1. Introduction evidence that the AAO trend is consistent with strato- spheric ozone loss over the past few decades. There has Analyses of observations over the last several decades also been considerable interest in the response of these suggest that the leading mode of variability of mean sea modes to greenhouse warming. Based on model simu- level pressure (MSLP) or 500-hPa geopotential height (Z500) modes in the mid- to high latitudes are the an- lations, Shindell et al. (1999) show that the observed nular modes (Mo and White 1985; Mo and Ghil 1987; AO trend can be attributed to greenhouse gas±induced Karoly 1990, 1995; Kidson and Sinclair 1995; Watter- warming, but they also ®nd that such a response only son 2000; Thompson and Wallace 1998, 2000; Hurrell exists in simulations with enhanced resolution in the 1995). These modes have been referred to as the Arctic stratosphere. Other studies indicate that the response of Oscillation (AO) for the Northern Hemisphere (NH) and the AO varies signi®cantly from one climate model to the Antarctic Oscillation (AAO) for the Southern Hemi- another (Kushner et al. 2001). In Fyfe et al. (1999), sphere (SH). Thompson and Wallace (2000) and suggest which uses a relatively coarse resolution in the strato- that the AAO and the AO are dynamically similar, and sphere, the trend of the AO is simulated but is much show that there have been trends in these two modes weaker than that in the Shindell et al. (1999) study. In over the past few decades with decreasing MSLP over the Geophysical Fluid Dynamics Laboratory warming the polar latitudes and increasing pressure in midlati- experiments, which are of comparable resolution to the tudes. Fyfe et al. (1999) integrations, there is no AO trend The forcing of the AO and AAO trends has received (Kushner et al. 2001). By contrast, the response of the considerable attention. Thompson and Solomon (2002) AAO to increasing CO2 displays a robust de®nite up- and Sexton (2001) provide observational and modeling ward trend in all transient greenhouse warming inte- grations. Most of the warming experiments (e.g., Fyfe et al. Corresponding author address: Dr. Wenju Cai, CSIRO Atmo- spheric Research, PMB 1, Aspendale, Vic 3195 Australia. 1999; Kushner et al. 2001) have the atmospheric equiv- E-mail: [email protected] alent CO2 concentration that increases according to an q 2003 American Meteorological Society Unauthenticated | Downloaded 10/06/21 09:47 AM UTC 1526 JOURNAL OF CLIMATE VOLUME 16 Intergovernmental Panel on Climate Change (IPCC) ice parameterization. One difference lies in the forcing scenario (Houghton et al. 1992; Michell et al. 1995; of the ocean spinup, in which the surface forcing ®elds Haywood et al. 1997). All scenarios include a transient have been modi®ed such that the annual cycle of sea period, in which the equivalent CO2 increases at a spec- surface temperature (SST) and sea surface salinity over i®ed rate from a reference level. So far, only the response the deep water formation regions are increasingly better of the AAO in the transient period has been studied. simulated from control 1 to control 3 (Bi et al. 2001). The subsequent behavior is yet to be explored. This is This results in a progressively stronger deep-penetrating the major focus of the present study. We analyze the North Atlantic deep water and more realistic water mass response of the atmospheric circulation simulated by the in the Southern Ocean from control 1 to control 3, yield- Commonwealth Scienti®c and Industrial Research Or- ing a strati®cation in control 3 that very closely matches ganisation (CSIRO) Mark 2 coupled GCM in three the observed structure (see Bi et al. 2001 for further warming runs all following the IPCC IS92a scenario. information). Another difference lies in the adjustment During the transient period, the equivalent CO2 increas- of the sea ice model (O'Farrell 1998), in which the es from 1860 to 2083 when the CO2 triples the level of sensitivity of sea ice to ocean heat exchange is made the pre-1860 level. All three warming runs then include more realistic, increasing from control 1 to control 3 a stabilization period of several centuries in which the (S. O'Farrell 2002, personal communication). As a re- CO2 is held at a constant, elevated 3 3 CO2 condition. sult, the sea ice amount in the control spinup state de- The rest of the paper is organized as follows. After creases from control 1 to control 3. describing the model and the experiments (section 2), Transient greenhouse warming runs are then con- we con®rm the upward trend of the model AAO during ducted using the three versions of the coupled model in the transient period and examine its subsequent behavior which the model is forced by increasing levels of green- during the stabilization period, which shows a gradual house gases as observed (1880±1990) and according to reversal (section 3). We demonstrate that the response IPCC scenario IS92a (1990±2100; Houghton et al. of the AAO is linked with that of the Southern Ocean 1992). The equivalent CO2 concentration doubles at (section 4), which is in turn associated with the feature about year 2048 and triples at year 2083 from the pre- of interhemispheric warming asymmetry (e.g., Stouffer 1880 level. Thus, in the model, the CO2 evolution rep- et al. 1989). resents the changes of all anthropogenic greenhouse gas- es in the IS92a scenario. The three runs will be referred to as run 1 (Hirst 1999), run 2 (Matear et al. 2000; 2. Model and model experiments Matear and Hirst 2002), and run 3 (Bi et al. 2001), as The CSIRO Mark 2 coupled model (Gordon and they start from control 1, control 2, and control 3, re- O'Farrell 1997) has a horizontal resolution of the R21 spectively. spectral representation, or approximately 3.28 latitude This period in which CO2 increases is referred to as 3 5.68 longitude, in both the atmosphere and ocean the transient period. Thereafter, each warming run is submodels. The atmospheric general circulation model continued for another several hundred years under a (GCM) has nine vertical sigma levels. It includes a semi- constant 3 3 CO2 condition. This period is referred to Lagrangian treatment of water vapor transport, dynamic as the stabilization period. At the time of analysis, the sea ice, and a bare soil and canopy land surface, as well shortest run had been continued for about 400 yr under as standard parameterizations of radiation, cloud, pre- the 3 3 CO2 condition. We shall compare the response cipitation, and the atmospheric boundary layer. The of the AAO in the three warming runs for the period ocean GCM has 21 vertical levels, and includes the that all three runs cover in common, that is, about 600 scheme of Gent and McWilliams (1990), which param- yr. Bi et al. (2001) described the response of the South- eterizes the adiabatic transport effect of subgrid-scale ern Ocean overturning in run 3. eddies, and replaces the nonphysical horizontal diffu- We apply empirical orthogonal function (EOF) anal- sivity as a means of stabilizing the model numerics. The ysis to outputs of annual-mean anomaly/change ®elds inclusion of the scheme results in a much improved of Z500 to identify major modes in all three of the strati®cation leading to a major reduction in convection control and warming runs. We choose this variable be- at high southern latitudes. A detailed description of the cause it is a commonly used ®eld, thus facilitating com- improvements has been given by Hirst et al. (2000) and parison with results of other studies in terms of modes the improvement in the high-latitude Southern Ocean simulated in the control runs. For the three control runs, has also been discussed by Cai et al. (2001). annual-mean anomalies are constructed from the long- The model experiments comprise three control cli- term mean (averaged over a 600-yr period).
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